### 抄録

Inference of the mantle viscosity from observations for glacial isostatic adjustment (GIA) process has usually been conducted through the analyses based on the simple three-layer viscosity model characterized by lithospheric thickness, upper- and lower-mantle viscosities. Here, we examine the viscosity structures for the simple three-layer viscosity model and also for the two-layer lower-mantle viscosity model defined by viscosities of η_{670,D} (670-D km depth) and η_{D,2891} (D-2891 km depth) with D-values of 1191, 1691 and 2191 km. The upper-mantle rheological parameters for the two-layer lower-mantle viscosity model are the same as those for the simple three-layer one. For the simple three-layer viscosity model, rate of change of degree-two zonal harmonics of geopotential due to GIA process (GIA-induced J˙_{2}) of -(6.0-6.5) × 10-11 yr^{-1} provides two permissible viscosity solutions for the lower mantle, (7-20) × 10^{21} and (5-9) × 10^{22} Pa s, and the analyses with observational constraints of the J_{2} and Last Glacial Maximum (LGM) sea levels at Barbados and Bonaparte Gulf indicate (5-9) × 10^{22} Pa s for the lower mantle. However, the analyses for the J˙_{2} based on the two-layer lower-mantle viscosity model only require a viscosity layer higher than (5-10) × 10^{21} Pa s for a depth above the core-mantle boundary (CMB), in which the value of (5-10) × 10^{21} Pa s corresponds to the solution of (7-20) × 10^{21} Pa s for the simple three-layer one. Moreover, the analyses with the J˙_{2} and LGM sea level constraints for the two-layer lower-mantle viscosity model indicate two viscosity solutions: η_{670,1191} > 3 × 10^{21} and η_{1191,2891} ~ (5-10) × 10^{22} Pa s, and η670,1691 > 1022 and η1691,2891 ~ (5-10) × 1022 Pa s. The inferred upper-mantle viscosity for such solutions is (1-4) × 1020 Pa s similar to the estimate for the simple three-layer viscosity model. That is, these analyses require a high viscosity layer of (5-10) × 1022 Pa s at least in the deep mantle, and suggest that the GIA-based lower-mantle viscosity structure should be treated carefully in discussing the mantle dynamics related to the viscosity jump at ~670 km depth. We also preliminarily put additional constraints on these viscosity solutions by examining typical relative sea level (RSL) changes used to infer the lower-mantle viscosity. The viscosity solution inferred from the far-field RSL changes in the Australian region is consistent with those for the J˙_{2} and LGM sea levels, and the analyses for RSL changes at Southport and Bermuda in the intermediate region for the North American ice sheets suggest the solution of η_{670,D} > 10^{22}, η_{D,2891} ~ (5-10) × 10^{22} Pa s (D = 1191 or 1691 km) and upper-mantle viscosity higher than 6 × 10^{20} Pa s.

元の言語 | 英語 |
---|---|

記事番号 | ggw301 |

ページ（範囲） | 719-740 |

ページ数 | 22 |

ジャーナル | Geophysical Journal International |

巻 | 207 |

発行部数 | 2 |

DOI | |

出版物ステータス | 出版済み - 11 1 2016 |

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### All Science Journal Classification (ASJC) codes

- Geophysics
- Geochemistry and Petrology

### これを引用

*Geophysical Journal International*,

*207*(2), 719-740. [ggw301]. https://doi.org/10.1093/gji/ggw301

**Inference of mantle viscosity for depth resolutions of GIA observations.** / Nakada, Masao; Okuno, Jun'ichi.

研究成果: ジャーナルへの寄稿 › 記事

*Geophysical Journal International*, 巻. 207, 番号 2, ggw301, pp. 719-740. https://doi.org/10.1093/gji/ggw301

}

TY - JOUR

T1 - Inference of mantle viscosity for depth resolutions of GIA observations

AU - Nakada, Masao

AU - Okuno, Jun'ichi

PY - 2016/11/1

Y1 - 2016/11/1

N2 - Inference of the mantle viscosity from observations for glacial isostatic adjustment (GIA) process has usually been conducted through the analyses based on the simple three-layer viscosity model characterized by lithospheric thickness, upper- and lower-mantle viscosities. Here, we examine the viscosity structures for the simple three-layer viscosity model and also for the two-layer lower-mantle viscosity model defined by viscosities of η670,D (670-D km depth) and ηD,2891 (D-2891 km depth) with D-values of 1191, 1691 and 2191 km. The upper-mantle rheological parameters for the two-layer lower-mantle viscosity model are the same as those for the simple three-layer one. For the simple three-layer viscosity model, rate of change of degree-two zonal harmonics of geopotential due to GIA process (GIA-induced J˙2) of -(6.0-6.5) × 10-11 yr-1 provides two permissible viscosity solutions for the lower mantle, (7-20) × 1021 and (5-9) × 1022 Pa s, and the analyses with observational constraints of the J2 and Last Glacial Maximum (LGM) sea levels at Barbados and Bonaparte Gulf indicate (5-9) × 1022 Pa s for the lower mantle. However, the analyses for the J˙2 based on the two-layer lower-mantle viscosity model only require a viscosity layer higher than (5-10) × 1021 Pa s for a depth above the core-mantle boundary (CMB), in which the value of (5-10) × 1021 Pa s corresponds to the solution of (7-20) × 1021 Pa s for the simple three-layer one. Moreover, the analyses with the J˙2 and LGM sea level constraints for the two-layer lower-mantle viscosity model indicate two viscosity solutions: η670,1191 > 3 × 1021 and η1191,2891 ~ (5-10) × 1022 Pa s, and η670,1691 > 1022 and η1691,2891 ~ (5-10) × 1022 Pa s. The inferred upper-mantle viscosity for such solutions is (1-4) × 1020 Pa s similar to the estimate for the simple three-layer viscosity model. That is, these analyses require a high viscosity layer of (5-10) × 1022 Pa s at least in the deep mantle, and suggest that the GIA-based lower-mantle viscosity structure should be treated carefully in discussing the mantle dynamics related to the viscosity jump at ~670 km depth. We also preliminarily put additional constraints on these viscosity solutions by examining typical relative sea level (RSL) changes used to infer the lower-mantle viscosity. The viscosity solution inferred from the far-field RSL changes in the Australian region is consistent with those for the J˙2 and LGM sea levels, and the analyses for RSL changes at Southport and Bermuda in the intermediate region for the North American ice sheets suggest the solution of η670,D > 1022, ηD,2891 ~ (5-10) × 1022 Pa s (D = 1191 or 1691 km) and upper-mantle viscosity higher than 6 × 1020 Pa s.

AB - Inference of the mantle viscosity from observations for glacial isostatic adjustment (GIA) process has usually been conducted through the analyses based on the simple three-layer viscosity model characterized by lithospheric thickness, upper- and lower-mantle viscosities. Here, we examine the viscosity structures for the simple three-layer viscosity model and also for the two-layer lower-mantle viscosity model defined by viscosities of η670,D (670-D km depth) and ηD,2891 (D-2891 km depth) with D-values of 1191, 1691 and 2191 km. The upper-mantle rheological parameters for the two-layer lower-mantle viscosity model are the same as those for the simple three-layer one. For the simple three-layer viscosity model, rate of change of degree-two zonal harmonics of geopotential due to GIA process (GIA-induced J˙2) of -(6.0-6.5) × 10-11 yr-1 provides two permissible viscosity solutions for the lower mantle, (7-20) × 1021 and (5-9) × 1022 Pa s, and the analyses with observational constraints of the J2 and Last Glacial Maximum (LGM) sea levels at Barbados and Bonaparte Gulf indicate (5-9) × 1022 Pa s for the lower mantle. However, the analyses for the J˙2 based on the two-layer lower-mantle viscosity model only require a viscosity layer higher than (5-10) × 1021 Pa s for a depth above the core-mantle boundary (CMB), in which the value of (5-10) × 1021 Pa s corresponds to the solution of (7-20) × 1021 Pa s for the simple three-layer one. Moreover, the analyses with the J˙2 and LGM sea level constraints for the two-layer lower-mantle viscosity model indicate two viscosity solutions: η670,1191 > 3 × 1021 and η1191,2891 ~ (5-10) × 1022 Pa s, and η670,1691 > 1022 and η1691,2891 ~ (5-10) × 1022 Pa s. The inferred upper-mantle viscosity for such solutions is (1-4) × 1020 Pa s similar to the estimate for the simple three-layer viscosity model. That is, these analyses require a high viscosity layer of (5-10) × 1022 Pa s at least in the deep mantle, and suggest that the GIA-based lower-mantle viscosity structure should be treated carefully in discussing the mantle dynamics related to the viscosity jump at ~670 km depth. We also preliminarily put additional constraints on these viscosity solutions by examining typical relative sea level (RSL) changes used to infer the lower-mantle viscosity. The viscosity solution inferred from the far-field RSL changes in the Australian region is consistent with those for the J˙2 and LGM sea levels, and the analyses for RSL changes at Southport and Bermuda in the intermediate region for the North American ice sheets suggest the solution of η670,D > 1022, ηD,2891 ~ (5-10) × 1022 Pa s (D = 1191 or 1691 km) and upper-mantle viscosity higher than 6 × 1020 Pa s.

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U2 - 10.1093/gji/ggw301

DO - 10.1093/gji/ggw301

M3 - Article

AN - SCOPUS:84994756811

VL - 207

SP - 719

EP - 740

JO - Geophysical Journal International

JF - Geophysical Journal International

SN - 0956-540X

IS - 2

M1 - ggw301

ER -